Palaeogene clinoform succession on Svalbard expressed in outcrops, seismic data, logs and cores

Johannessen, Erik P.; Henningsen, Tormod; Bakke, N.E.; Johansen, Tor Arne; Ruud, B.E.; Riste, P.; Elvebakk, Harald; Jochmann, Malte; Elvebakk, G.; Woldengen, M.S.

doi:10.3997/1365-2397.2011004

Cited by 23 publications

(27 citation statements)

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“…The Frysjaodden Formation is up to 450 m thick and is dominated by mudstones of prodelta slope to basin‐floor origin. Along the western margin of the Central Basin, the formation includes several intercalated sandstone wedges emplaced by various sediment gravity flow processes (Steel et al ., ; Johannessen & Steel, ; Johannessen et al ., ). These sandstone wedges are the focus of this study, and are referred to collectively as the Bjørnsonfjellet Member (Steel et al ., ; Fig.…”

Section: Geological Settingmentioning

confidence: 97%

Depositional architecture and evolution of progradationally stacked lobe complexes in the Eocene Central Basin of Spitsbergen

Grundvåg¹,

et al. 2013

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The down-dip portion of submarine fans comprises terminal lobes that consist of various gravity flow deposits, including turbidites and debrites. Within lobe complexes, lobe deposition commonly takes place in topographic lows created between previous lobes, resulting in an architecture characterized by compensational stacking. However, in some deep water turbidite systems, compensational stacking is less prominent and progradation dominates over aggradation and lateral stacking. Combined outcrop and subsurface data from the Eocene Central Basin of Spitsbergen provide a rare example of submarine fans that comprise progradationally stacked lobes and lobe complexes. Evidence for progradation includes basinward offset stacking of successive lobe complexes, a vertical change from distal to proximal lobe environments as recorded by an upward increase in bed amalgamation, and coarsening and thickening upward trends within the lobes. Slope clinoforms occur immediately above the lobe complexes, suggesting that a shelfslope system prograded across the basin in concert with deposition of the lobe complexes. Erosive channels are present in proximal axial lobe settings, whereas shallow channels, scours and terminal lobes dominate further basinward. Terminal lobes are classified as amalgamated, non-amalgamated or thin-bedded, consistent with turbidite deposition in lobe axis, offaxis and fringe settings, respectively. Co-genetic turbidite-debrite beds, interpreted as being deposited from hybrid sediment gravity flows which consisted of both turbulent and laminar flow phases, occur frequently in lobe off-axis to fringe settings, and are rare and poorly developed in channels and axial lobe environments. This indicates bypass of the laminar flow phase in proximal settings, and deposition in relative distal unconfined settings. Palaeocurrent data indicate sediment dispersal mainly towards the east, and is consistent with slope and lobe complex progradation perpendicular to the NNW-SSE trending basin margin.

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Section: Geological Settingmentioning

confidence: 97%

Depositional architecture and evolution of progradationally stacked lobe complexes in the Eocene Central Basin of Spitsbergen

Grundvåg¹,

et al. 2013

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“…For example, the Eocene-age succession outcropping in Spitsbergen hosts both gently-dipping low-relief (tens of metres) shoreline clinoforms and more steeply-dipping (3-6°), highrelief (average 200 m) sandy shelf-edge clinoforms. Regressive-transgressive shoreline cycles across narrow (1-10 km) and shallow (< 50 m) shelves are reflected by the alternate deposition of actively accreting sand-prone shelf-edge delta clinothems and, after each transgression, mudstone-prone shelf-edge draping clinothems (HellandHansen, 1992(HellandHansen, , 2010Helland-Hansen et al, 1994;Steel et al, 2000Steel et al, , 2003Steel and Olsen, 2002;Mellere et al, 2002;Johannessen and Steel, 2005;Uroza and Steel, 2008;Johannessen et al, 2011;Grundvåg et al, 2014) (Fig. 14D).…”

Section: Shelf-edge Scale Clinoforms (Figs 14-16)mentioning

confidence: 99%

Clinoforms and clinoform systems: Review and dynamic classification scheme for shorelines, subaqueous deltas, shelf edges and continental margins

Patruno

Helland‐Hansen

2018

Earth-Science Reviews

185

166

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A B S T R A C TClinoforms are inclined and normally basinward-dipping horizons developed over a range of spatial and temporal scales in both siliciclastic and carbonatic systems. The study of clinoform successions underpins sequence stratigraphy and all efforts to reconstruct the relative partitioning of reservoir, seal and source rocks along shoreline to basin-floor profiles.Here, we review clinoform research and propose a more systematic description and classification of clinoforms. This is a crucial step to improve predictions of facies and lithology distribution within shoreline to continental shelf and abyssal plain successions, together with the genesis, drivers and dynamics of their constituent sedimentary units.Four basic clinoform types are here distinguished in delta/shorelines, lacustrines and marine environments, on the basis of their overall spatial and temporal scale, morphology, outbuilding dynamic and geodynamic and depositional setting: (1, 2) delta-scale clinoforms, which in turns are sub-divided into shoreline and delta-scale subaqueous clinoforms; (3) shelf-edge clinoforms; and (4) continental-margin clinoforms. Delta-scale clinoform sets are tens of metres high and typically represent 1-10 3 kyr, with progradation rates ranging from 1,000-100,000 m/kyr for shorelines and "subaerial deltas" to 100-20,000 m/kyr for subaqueous deltas; shelfedge clinoform sets are hundreds of metres high and are nucleated and accreted in 0.1-20 Myr (usual progradation rates of 1-100 m/kyr) by successive cross-shelf transits of delta-scale clinoforms; continental-margin clinoform sets are thousands of metres high, hallmark key geodynamic/crustal boundaries (e.g., continent/ocean transition) and slowly prograde basinwards in ca. 5-100 Myr, with typical rates of 0.1-10 m/kyr. As a consequence of the very different progradation rates and of the difficulty of large-scale clinothems to backstep during transgressions, shorelines are the most dynamic clinoforms with regards to position, continental margins the least, and shelf-edges are intermediate. Shortly after a transgression, therefore, the four clinoform types may prograde synchronously along shoreline-to-abyssal plain transects, forming "compound clinoform" systems. During the subsequent regressive cycle, however, due to the dissimilarity in progradation rates, different clinoform types will normally merge progressively with each other, giving rise to "hybrid clinoforms" (e.g., shelf-edge deltas), and fewer depositional breaks-in-slope are distinguished along a single shoreline-toabyssal plain transect. Overall, all clinoform systems are the result of the dynamic evolution of compound and hybrid clinoforms along a temporal and spatial continuum, regulated by the cyclical backstepping of the smallerscale system within natural progradational-retrogradational cycles of larger-scale clinothem outbuilding.All clinothem types may show either an accretionary/active or draping/passive style, depending on the proximity to the sediment source. Draping clinothems are nearly...

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“…2), one onshore twodimensional (2D) seismic line crossing the well (Fig. 3;Johannessen et al, 2011), and extensive ground-based and helicopter-based photography coverage of the main outcrops. Outcrop measurements include descriptions of rock type, grain-size, sorting, sedimentary structures, body and trace fossils and palaeocurrent data.…”

Section: Data Set and Methodsmentioning

confidence: 99%

“…1Dfor location of seismic line and well. Seismic line annotation modified fromJohannessen et al (2011).…”

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confidence: 99%

The depositional architecture and facies variability of shelf deltas in the Eocene Battfjellet Formation, Nathorst Land, Spitsbergen

Grundvåg¹,

Helland‐Hansen

Johannessen

et al. 2014

Sedimentology

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Deltas are commonly classified according to their plan‐view morphology as either river‐dominated, tide‐dominated or wave‐dominated. However, most deltas form under the mixed influence of these processes, commonly with laterally varying process regimes. It has also become clear that there is a mismatch between the plan‐view morphology and internal facies composition in some deltas. Combined outcrop and subsurface data from the Eocene Battfjellet Formation, Spitsbergen, provide an example of ancient shelf deltas that formed under mixed influence. Internally, these shelf deltas are characterized by wave‐dominated facies that are normally associated with strike‐extensive, nearly linear shoreline sandstones. However, the formation comprises partially overlapping sandstone bodies of limited lateral extent (<20 km in any direction). This stacking pattern is attributed to frequent autogenic lobe switching that caused localized and rapid transgressions. Such processes typify fluvial‐dominated deltas and occur less commonly in wave‐dominated ones. Thus, there is an apparent mismatch between inferred plan‐view morphology and internal facies composition. It is argued that the Battfjellet deltas were flood‐dominated and prograded mainly during periods of high fluvial discharge. However, reworking of the fluvial‐flood facies by fair‐weather and storm waves, as well as longshore currents, resulted in a wave‐dominated facies character. Delta lobes undergoing auto‐retreat were particularly prone to reworking by basinal processes, including tidal currents. It is suggested that repeated delta progradation from inner shelf settings towards the outer shelf and shelf edge was aided by high sediment supply rather than relative falls in sea‐level as previously suggested. This interpretation is supported by: (i) the lack of major facies dislocations and extensive sub‐aerial unconformities; and (ii) an overall relative rise in sea‐level as evidenced by an overall low‐angle (0·8 to 1·2°) ascending shoreline trajectory. The latter results from the combined effect of basin subsidence, eustatic highstand and sediment compaction.

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Palaeogene clinoform succession on Svalbard expressed in outcrops, seismic data, logs and cores

Cited by 23 publications

References 0 publications

Depositional architecture and evolution of progradationally stacked lobe complexes in the Eocene Central Basin of Spitsbergen

Depositional architecture and evolution of progradationally stacked lobe complexes in the Eocene Central Basin of Spitsbergen

Clinoforms and clinoform systems: Review and dynamic classification scheme for shorelines, subaqueous deltas, shelf edges and continental margins

The depositional architecture and facies variability of shelf deltas in the Eocene Battfjellet Formation, Nathorst Land, Spitsbergen

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